Tabara_ Chirila _PALAEOCLIMATIC ESTIMATION FROM MIOCENE OF ROMANIA, BASED ON PALYNOLOGICAL DATA

8/2/2019 Tabara_ Chirila _PALAEOCLIMATIC ESTIMATION FROM MIOCENE OF ROMANIA, BASED ON PALYNOLOGICAL DATA

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Carpathian Journal of Earth and Environmental Sciences, May 2012, Vol. 7, No. 2, p. 195 - 208

PALAEOCLIMATIC ESTIMATION FROM MIOCENE OF ROMANIA,BASED ON PALYNOLOGICAL DATA

Daniel ABR1 & Gabriel CHIRIL11Al. I. Cuza University of Iai, Department of Geology, 20A Carol I Blv., 700505 Iai, Romania.

[email protected],[email protected]

Abstract: Few climatic parameters available for the stratigraphic interval between Aquitanian Pontianfrom Romania, have been obtained after analysis of the palynological associations using the CoexistenceApproach. The results obtained for MAT (mean annual temperature), MAP (mean annual precipitations),WMT (mean temperature of the warmest month), CMT (mean temperature of the coldest month), have

been synthesised and palaeoclimatic diagrams have been plotted, revealing visible climatic fluctuation forthe analysed interval. Palaeoclimatic curve was calculated for Dacian Basin, covering the southern andeastern part of Romania and Transylvanian Basin (Central-Western area of the country). MAT with high

value have been observed for the Burdigalian (approximately 18.4C), then a general trend of cooling wasobserved. The calculated values of MAP from the Miocene reach from 9571353 mm. Beginning with the

Late Miocene, a slight cooling and some drying is recorded in Dacian Basin due to a regional palaeogeographic reorganizations and tectonic processes. Our study provides a new insight intopalaeoclimatic evolution from Romania, based on palynological data.

Keywords: palynology, palaeoclimate reconstruction, Coexistence approach, Miocene, Paratethys,Romania.

1. INTRODUCTION

The Paratethys Domain began was formed in

early Oligocene as result of a collision movements

of Afro-Arabian plate and Eurasian plate in Alpine

tectonics (Allen and Armstrong, 2008). At the end of

the Lower Miocene this great epicontinental sea was

separated into three sub-basins, namely Western,

Central and Eastern Paratethys (Ivanov et al., 2010).

Palynological assemblages analyzed in this

paper are distributed in marine and freshwater

basins, belonging to the eastern part of CentralParatethys (Transylvanian Basin) and western part

of Eastern Paratethys (Dacian Basin) (Fig. 1).

During Lower Miocene, the Dacian Basin was

not configured as a unit with its own complex,

separation as basin occurred during Middle

Sarmatian (Saulea et al., 1969). Due to reduction of

communication with the Mediterranean Basin the

salinity decreased and the brackish water area

gradually retreating toward Euxinian Basin. The

complete silting of the Dacian Basin occurred during

Middle Dacian.

Transylvanian Basin is an intra-Carpathian

episutural Basin with Upper Cretaceous- Neogene

age, which had a roughly circular form during Upper

Miocene - Pliocene (Krzsek and Filipescu, 2005).

This is located within the Carpathian area being

separated by Pannonian Basin by the Apuseni

Mountains (Fig. 1). The sedimentary filling of the

basin has a thickness of over 5000 m (Ciupagea et al.,

1970) and was divided into four tectonostratigraphic

megasequences (Krzsek and Bally, 2006): Upper

Cretaceous (rift), Paleogene (sag), Lower Miocene

(flexural basin) and Middle to Upper Miocene(backarc sequence dominated by gravitational

tectonics).

The main objective of this study was to offer a

synthesis of palynological data from the Miocene

period of Romania. Palaeoclimatical reconstruction

from this paper was accomplished applying on

bibliographical data (20 palynological assemblages)

and own studied palynofloras (16 assemblages)

(Table 1). One palynological assemblages consists

of many taxa (view in 20-30 palynological slides),

the same age, identified in different geographical

locations.

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Figure 1. Palaeogeographic sketch-maps of the Paratethyan area (after Rgl, 1998; Harzhauser & Piller, 2007).

Until now, in Romania, this type of

reconstructions was based on macrofloras from

Transylvanian Basin, accomplished by Givulescu

(1997) (MAT for the interval between Upper Eocene

Lower Pleistocene). Using microfloras, the MAT

(mean annual temperature) for the interval

Paleocene Pliocene was determined by Petrescu &

Balintoni (2004).

The authors previously cited, presented a

curve of the altitudinal variations of the Romanian

Carpathians on the same stratigraphic interval, in the

same paper. In the Moldavian Republic,

palaeoclimatical reconstructions (MAT, MAP -

mean annual precipitations, CMT - mean

temperature of the coldest month, WMT - mean

temperature of the warmest month) have been

obtained from the analysis of a macroflora from the

interval between Sarmatian and Maeotian bytefr (1997).

In the past decade, several palaeoclimatical

reconstructions based on Neogene palaeoflora from

the Paratethys area have been completed by Ivanov

et al. (2002, 2007a, 2010); Jimnez-Moreno et al.

(2005); Bruch et al. (2006, 2007); Utescher et al.

(2007); Erdei et al. (2007); Syabryaj et al. (2007);

Kayseri and Akgun (2008); Bozukov et al. (2009).

2. MATERIALS AND METHOD

36 palynological assemblages (Table 1) wereused for the present palaeoclimatic estimations.

They originate from the Miocene deposits

encountered in outcrops and drilled wells from

Moldova, Transylvania, South Dobrogea, Oltenia

and Banat area (Fig. 2).

Microfloristic data sets concerning

Aquitanian, Burdigalian, Badenian and Pontian have

been taken from publications by Petrescu et al.

(1990, 1997, 1998, 2001, 2002); Petrescu (2003);

Stoicescu (2004); Brian (2004); Gu-Popescu

(2006) (Table 1). The palaeoclimatical interpretation

of the Sarmatian was performed on the based on the

analysis of newly collected samples from the

Moldavian Platform. Data regarding the Maeotian

are missing from our paper due to the lack of

microfloristic inventory for this time slice in

Romania.

We applied the Coexistence Approach (CA)

method (Mosbrugger & Utescher 1997) for all the

36 palynological associations. This method is used

for quantitative terrestrial palaeoclimate

reconstructions for the Cenozoic. It relies on the

assumption that fossil plant taxa have similar

climatic requirements as their nearest living

relatives. The aim of the coexistence approach is to

find an interval for a given fossil flora and a given

climate parameter, in which all nearest living

relatives of the fossil flora can coexist.

Figure 2. Geographical location of palynologicalassemblages used for this paper (detailed explanations is

presented in Table 1).

Palaeoclimatic estimations obtained are based

on climatic requirements (minimum and maximum

values for MAT, MAP, CMT, WMT) of 70 taxa

(Plate 1 - 3). These values of the coexistence

intervals have been taken from Gebka et al. (1999);

Olivares et al. (2004); Kou et al. (2006); Akkiraz et

al. (2006, 2008), Mosbrugger and Utescher (2010,

personal communication) and palaeoflora database

(http://www.palaeoflora.de).

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The quantity of sediments for the analysis was

approximately 50 g for each sample (this method

was applied for the 16 palynological assemblages

cited in abr, Olaru, 2004; Brnzil, abr, 2005;

Chiril, abr, 2008; abr 2008, see Table 1).

Samples have been treated with HCl (37%) to

remove the carbonate and HF (48%) to remove the

silicate minerals. The separation of palynomorphsfrom the residue resulting from the chemical

reaction above described was performed using ZnCl2

with a density 2.00 g/cm3

as heavy liquid with

centrifugal action. Microscopic slide were made

using glycerine jelly as a mounting medium. The

visualisation of the palynomophs was accomplished

with a Leica DM1000 microscope, using the

amplification of X100, X400.

3. PALAEOCLIMATE RECONSTRUCTION

The present study is based on 4 palaeoclimatic

parameters:

- Mean annual temperature (MAT)

For this basin, Petrescu (1994) have described

a palynological assemblage with Middle Aquitanian

age from Dealul Cotului Formation (North-Western

Transylvania) (Fig. 2). Since this period, a slight

increase of MAT, MAP and CMT was observed,

compared with analyzed deposits of Lower

Aquitanian from East Carpathian Flysch. (Figs. 3, 4,

5). The obtained values are following: MAT between

15.7 18.4C (approximately 17C), MAP between

1122 1281 mm and CMT varies between 9.6

12.5C. For the same palynoflora, Petrescu (2003)

establishes a MAT of approximately 17C. Another

palynological association with Upper Aquitanian age

was cited from the South-Eastern part of the Haeg

Basin by Petrescu & Popescu (2002). The calculation

of MAT, MAP, CMT and WMT from thisstratigraphic interval indicates values naerly identical

in both palynological association (Dealul Cotului

Formation and Haeg Basin).

- Mean annual precipitation (MAP)

- Mean temperature of the warmest month

(WMT)

- Mean temperature of the coldest month

(CMT)

Palaeoclimatic diagrams resulting from the

obtained data have revealed oscillations of the MAT,

MAP, CMT, WMT (Figure 3, 4, 5, 6) from the

Aquitanian Pontian of Romania. These valueshave been compared to palaeoclimatic data obtained

from the Romanian Miocene (Givulescu 1997),

North-Western and West of Bulgaria (Ivanov et al.

2002, 2007b), Serbia (Utescher et al. 2007) and

Pannonian Basin from Hungary (Erdei et al. 2007).

3.1. Lower Miocene

3.1.1. Dacian Basin.Palaeoclimatic data from Oligocene-Miocene

limit were obtained from analyzed samples of Upper

Dysodilic Shale Formation (Stoicescu, 2004). Thecoexistence interval for MAT values based on

palynological assemblage is between 13.3 17.2C

and MAP value is between 5781520 mm. The

CMT is 0.9 7C and WMT value range between

23.6 28.1C (Table 1). Regarding the end of

Oligocene (Chattian), Petrescu (2003) observed an

invasion of temperate taxa which indicates a

cooling of climate. The same cooling at the Chattian

Aquitanian boundary was observed by Givulescu

(1997) based on palaeofloras from Valea Jiului

(MAT value calculated was 15C).

The climatological data used for Burdigalian

was acquired from Gura oimului Formation, Lower

Salifer Formation and Hrja Formation from Slnic

Oituz Half-Window which belongs to the Eastern

Carpathian Flysh. The highest values of MAT, MAP

and CMT were recorded for Gura oimului

Formation (Figs. 3, 4, 5). Palaeoclimatic data

calculated for studied microflora from Guraoimului Formation show a MAT with a value of

15.6 21.3C, MAP range between 897 1613 mm

and CMT value is 9.6 16.3C. As shown in figure

3, the value of MAT calculated for Burdigalian are

higher than those from Aquitanian.

3.1.2. Transylvanian Basin

Mean annual temperatures calculated by

Givulescu (1997) for the pluvial subtropical forest

with Lauraceae from Coru (Cluj) with Upper

Aquitanian age, indicate higher values by

approximately 2C compared to temperatures

presently calculated from Aquitanian microflora

using the Coexistence approach (Fig. 3). Obtained

MAT data for Aquitanian deposits from Pannonian

Basin (Erdei et al., 2007) are comparable with valuescalculated by us from Transylvanian Basin (Fig. 3).

Palynological assemblages with Burdigalian age

used for palaeoclimatic estimation are located in the

Western part of Romania, in the Bozovici and Borod

Basin (Fig. 2). The highest values of MAT

(approximately 17.8C) and MAP (approximately

1353 mm) were observed in Lower Burdigalian

deposits from Borod Basin (North-Western

Transylvanian Basin). The Burdigalian macroflora

from North-Western part of Transylvanian Basin has

previously been cited by Petrescu (1969) at Tihu

(Slaj county).

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Figure 3. The trend of climate variables (MAT) from the Miocene of Romania, correlated with other palaeoclimaticcurves obtained from the same stratigraphic interval from the North-West of Bulgaria, Serbia and Hungary. The drawncurves represent the average of the coexistence interval. 1, 236, palynological assemblages analysed (see explanation

in Table 1).

Figure 4. The variation of the MAP from the Miocene of Romania, correlated with other palaeoclimatic curves obtainedfrom the same stratigraphic interval from the North-West of Bulgaria, Serbia and Hungary. The drawn curves represent

the average of the coexistence interval. 1, 236, palynological assemblages analysed (see explanation in Table 1).

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Figure 5. The palaeoclimatic chart for CMT value from Miocene deposits of Dacian and Transylvanian Basin. 1, 236,

palynological assemblages analysed (see explanation in Table 1).

Figure 6. The values of WMT obtained based on palynological assemblages from Miocene deposits of Romania (see

explanation in Table 1).

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Several arctotertiary taxa which indicate an MAT

with value between 15.5 - 16C have been identified

in this location. Similar values of MAT, MAP and

WMT obtained from Burdigalian deposits of

Transylvanian Basin have been presented from

deposits with the same age from Pannonian Basin

(Erdei et al., 2007).

3.2. Middle Miocene

3.2.1.Dacian BasinMiddle Miocene is between Lower Badenian

and Middle Bessarabian (16.3 11.6 Ma)

(Harzhauser and Piller, 2007). The MAT value of

Middle Miocene microflora from Dacian Basin

marks a gradual decrease compared to values

calculated for Burdigalian deposits (Fig. 3).

Palaeoclimatic values from the Upper

Badenian derive from interpretation ofibrinu andGherghina microflora (South Dobrogea). Therefore,

MAT value was estimated between 15.6 17.2 C

and MAP range between 897-1281 mm (Table 1).

Also, the microflora from the Trueti and Ivncui

(Northern Moldavian Platform) have an Upper

Badenian age. The value of MAT calculated based

on above palynological assemblages indicates a

temperature increase to about 18C, and MAP was

between 897 1520 mm. This last increase of MAT

during Upper Badenian was also presented in North-

Western Bulgaria (MAT of 17.5C, according with

Ivanov et al., 2002).To the East, in the Ukraine Plain (Korobki

region), Syabryaj et al. (2007) estimated for Upper

Badenian a MAT of 15.6 C and the MAP between

1304 1356 mm.

Palaeoclimatical estimation for Volhynian and

early Bessarabian period was performed analysing

from deposits mainly of the Moldavian area

(Moldavian Platform) (Chiril and abr, 2008,

2010; abr, 2008). At the end of Badenian and the

beginning of the Sarmatian, MAT decreased by

approximately 1,5C (Fig. 3), showing values

between 16.4 - 17C for the Volhynian and earlyBessarabian from Moldavian area. The same slight

decrease was observed for CMT values, from 10 to

12C durring Upper Badenian at approximately 6 -

8C in Volhynian and Lower Bessarabian (Fig. 5).

Palaeoclimatic values calculated for WMT had small

variation during Badenian and Lower and Middle

Sarmatian (Fig. 6).

In the Moldavian Republic, palaeoclimatic

estimations for a Volhynian palaeoflora have shown

a climate similar to the actual climate from western

Mediterranean Sea: MAT of approximately 15C,

WMT 25C, CMT 36C and MAP of

approximately 1000 mm (tefr 1997). For the

Bessarabian from the same area, tefr establish

following climatic parameters: MAT 11 C, WMT

23 C, CMT with value higher than -2 C and MAP

with maximum 700 mm. According with data

presented by author, a drop in MAT by 4 C

between Volhynian and Bessarabian is visible. This

difference in temperature was not observed in the

present palynological analysis.

3.2.2. Transylvanian BasinPalynological association from L pugiul de

Sus, Ocna Dej, Turda, Srel and Praid with

Badenian age of Transylvanian Basin are

interpreted.

The Lower Badenian from L pugiul de Sus

(Petrescu et al., 1990) indicates MAT with value

around 17C, the deposits from this area yield a

subtropical marine fauna, characterised by presence

of colonial hexacorals (Heliastrea). The MAP of theancient bay from Lpugiu was found to range from

1800 2000 mm (Petrescu, 2003) and

approximately 1230 mm according with our

estimations.

Palaeoclimatic estimations for Middle

Badenian (Wieliczian) have been assumed after the

analysis of the microflora from salt deposits of Ocna

Dej, Turda, Srel and Praid. The MAT for the area

cited above, in our opinion, ranged between 16 -

17C, MAP 1089 1270 mm, CMT approximately11C and WMT 26,3C. Petrescu and Brian (1997)

observe a climatical transition for the Wieliczian

between Lower Badenian (subtropical-warm) and

Upper Badenian (temperate-warm climate), which

reveals a neogenisation of the microflora.

The BadenianSarmatian limit from Transylvanian

Basin correspond to a slight thermal regress assumed

by Petrescu et al. (1988) who calculated the MAT

from Mereti-Harghita to a value of 15C. The same

regress of MAT from the limit previously cited was

observed by Givulescu (1997) in Transylvanian area.

According to this author, the stratigraphic interval

between Lower Sarmatian and Pannonian, belongs

to a domain with pluvial temperate-warm climate

and oscillation in precipitation amounts which vary

from seasonally dry to moist, wet and rainy.

In Hungary, Nagy (1992) for Lower

Sarmatian (13 13.5 Ma) has established a

minimum of subtropical and tropical taxa, the last

ones disappearing from this area in Lower

Pannonian (= Upper Bessarabian Chersonian).

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Plate 1. 1. Pinus haploxylon type (Cathaya); 2.Pinus diploxylon type; 3. Sciadopitys sp.; 4.Picea sp.; 5. Tsuga sp.; 6.Abies sp.; 7.Ephedra sp.; 8. Taxodium; 9. Taxodioideae; 10. Osmunda sp.; 11.Pteris sp.; 12, 13Engelhardia sp.

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Plate 2. 1. Cedrus sp.; 2. Cyrilla sp.; 3. Chenopodiaceae; 4.Ilex sp.; 5, 6 Myricipites sp.; 7.Liquidambarsp.; 8.Fagussp.; 9. Carpinus sp.; 10.Palmae; 11. Cissus / Parthenocissus; 12. Carya sp.; 13.Juglans sp.; 14. Magnolia sp.; 15. Tilia

sp.; 16.Betula sp.; 17.Alnus sp.; 18. Castanea sp.; 19.Nyssa sp.; 20, 21 Quercus sp.; 22. Symplocos sp.; 23.Acersp.

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Plate 3. 1. Mastixiaceae; 2.Pterocarya sp.; 3. Sapotaceae; 4. Quercus sp.; 5. Ulmus sp.; 6.Zelkova sp.; 7. Sphagnum

sp.; 8. Sparganium / Typha.

3.3. The Late Miocene

3.3.1.Dacian BasinIn Eastern Paratethys, the Miocene period is

between Upper Bessarabian (11.6 Ma) and Upper

Pontian (5.3 Ma) (Popov et al., 2006; Harzhauser

and Piller, 2007).

Palaeoclimatic estimations from UpperBessarabian and Chersonian have been assumed by

us, based on a microflora from North-Eastern

Dacian Basin (Moldavian Platform) (abr, 2008).

The Upper Bessarabian deposits from this area has

similar palaeoclimatic values with those from upper

part of Middle Miocene. Palaeoclimatic parameters

have following values: MAT of 16.4 17C, MAP

1052 1234 mm, CMT between 5.8 8.7C and

WMT with a value of 26.5C.

The BessarabianChersonian limit represents

the beginning of few climatic changes in Moldavian

Platform and not only. Based on this study, we

conclude that beggining with 10 - 11 Ma. ago, the

climate from this region has a decreasing of the

MAT (with 1,5C), MAP and WMT (Fig. 3, 4, 6).

Unlike the regression of climatic parameters cited

above, the average of temperatures in winter (CMT)

are roughly similar to those calculated from Upper

Bessarabian. As the cause of this cooling at the

Bessarabian Chersonian limit, we have examined

two possible aspects: the volcanic eruptions from

Eastern Carphatians at the beginning of the

Chersonian (the sedimentation moment of the

Nuasca-Ruseni tuff) and higher altitudinal values of

the same mounts (approximately 2400 m, after

Petrescu & Balintoni 2004) which may have

conditioned these periods of cooling. We have to

specify that some Chersonian palynological

associations identified in Paiu Quarry and Oeleni

(both sites situated in Vaslui county, Fig. 2) (abr

2008) did not offer enough taxa for palaeoclimaticestimations.

A decrease in MAT and MAP at the

Bessarabian Chersonian limit, was observed also

in North-West Bulgaria by Ivanov et al. (2002). An

increase in percentage of the Chenopodiaceaepollenis also mentioned in the Upper Bessarabian

palynological spectra which will become more

abundant in Chersonian (up to 16%). This

xerophytic herbaceous association which covered

open landscapes was also identified in Upper

Bessarabian from Moldavian Platform, in

Cryptomactra Formation (abr 2008).

The appearance of this xerophytic vegetation

was possible with the decrease of the Sarmatic Sea

level from North-West to South-East during the

Bessarabian in Moldo-Galiian Gulf.

The climatic parameters established for

Volhynian and Bessarabian from Bulgaria show the

following values (Ivanov et al. 2002): MAT between

15.617.2C, CMT 57 C and WMT 24.627.8C.

For Chersonian a lower MAT with 2C was

calculated regardless with the Bessarabian and

Volhynian. The same cooling was observed by the

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authors for CMT and WMT curves (Figs. 5, 6). In

this paper, palaeoclimatic estimations revealed by

microfloristic content with Maeotian age cannot be

obtained because such associations are absent. Some

climatic parameters obtained after the analysis of a

Maeotian macroflore have been mentioned by

Stefr (1997). From the Seimen outcrop (south of

Moldavian Republic), the author cites few taxacharacteristics for an temperate broadleaf forest

which vegetate in climatic conditions specific for an

relative warm region of the temperate area, having

MAT of approximately 9C and MAP 700800 mm.

In the East of the Moldavian Republic, Syabryaj et

al. (2007) mentioned the following climatic

parameters for Lower Maeotian from southern

Ukrainian plain: MAT coexistence interval between

4.917.4C; CMT between -0.110.2C; WMT

between 17.127C and MAP between 389971

mm. For North-West Bulgaria, Ivanov et al. (2002)

mentioned for Maeotian a MAT of approximately

16C and oscillations of MAP between 9001150

mm. From the Serbian Republic (the southern part of

Pannonian Basin System), for the same period,

Utescher et al. (2007), established a MAT of

approximately 15C and MAP of 1150 mm.

Palaeoclimatic estimations for Pontian have

been made after analysis of palynological

assemblages from South-West Romania (Batoi -

Mehedini and Valea Vienilor - Mehedini county,

Petrescu et al. 2001, 2002). Using the Coexistenceapproach for the previously cited palynological

association reveals a MAT of approximately 16.4

17.2C and MAP 1234 - 1258 mm (coexistence

interval between 1162 - 1355 mm) in Pontian (Table

1). The CMT for the mentioned period was

approximately 5.8C and WMT about 26C.

Similar values of MAT for the North-Western

part of Bulgaria have been obtained by Ivanov et al.

(2002). According to data presented by the author

for the Lower Pontian, the value of the coexistence

interval for MAT was 15.617.2C, CMT 57C and

MAP 11871308 mm. From Western Bulgaria

(Ivanov et al., 2007b) present palaeoclimatic values.

approximately equal to those calculated by us for the

South-Western of Romania (Figs. 3, 4, 5, 6). Based

on a Upper Pannonian Pontian palaeoflora

identified in central part of Serbia (Crveni Breg

Grocka area) and in the Western part of this country

(Osojna-Kladovo), Utescher et al. (2007) established

a value of MAT lower with 1.5-2 C (14.8C),

comparative with ours and Ivanov et al. (2002,

2007b) results. The precipitation regime of the

Upper Pannonian Pontian from Serbia (the central

a nd western part) was comprised in the coexistence

interval 8971297 mm, CMT between -0.15.8C

and WMT between 25.726.7C. Pontian climatic

parameters from the Ukrainian plain (locality

Chaplinka, at approximately 50 km at north of

Danube Delta) show lower values than previously

cited data, with a MAT between 13.814.5C, WMT

2324,1C and MAP 8971151 mm (Syabryaj et al.,

2007).

4. CONCLUSIONS

Climatic parameters assumed in present paper

have been obtained using Coexistence approach,

applied on a number of 36 palynological

assemblages from the Miocene of Romania. Those

associations have been highlighted from eastern part

of Central Paratethys (Transylvanian Basin) and

western part of Eastern Paratethys (Dacian Basin).The lower part of Miocene shows a slight

increased of palaeoclimatic parameters compared

with the end of Oligocene, to a MAT value of

18,4C during sedimentation of Gura oimului

Formation (Slnic-Oituz Half-Window). In

Transylvanian Basin, the highest values of MAT

(approximately 17.8C) and MAP (approximately

1353 mm) have been calculated for Borod area with

Burdigalian age.

The microflore from Middle Miocene deposits

of Dacian Basin from South Dobrogea (Gherghina

and ibrinu) indicate a value of MAT between 15,6 17,2C and MAP of 897 1281 mm. The Upper

Badenian from northern Moldavian Platform

indicates a slight increase of MAT to approximately

18C and a MAP between 897 1520 mm. The

Lower Sarmatian from the same area shows a

decrease of MAT with approximately 1.5C

compared with Badenian values.

Palaeoclimatic estimation of Badenian

deposits from Transylvanian Basin indicates a MAT

with gradual decrease from its base to the top of this

age. The Badenian - Sarmatian limit correspond, asin Dacian Basin, to a slight thermal regress of MAT

reaching at 15C in the lower part of the Sarmatian

deposits from Mereti-Harghita.

Palaeoclimatic values at the beginning of the

Upper Miocene come from the interpretation of a

microflore from North-Eastern part of Dacian Basin

(Moldavian Platform). The climatic parameters of

Upper Bessarabian have approximately similar

values to those identified in the upper part of the

Middle Miocene. The MAT value was 16.4 17 C,

MAP 10521234 mm, CMT between 5.8 to 8.7 C

and WMT values was 26.5 C.

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A particularity of the palaeoclimatic evolution

of the Late Miocene is represented by the

BessarabianChersonian transition from Moldavian

Platform. Due to volcanic eruptions along the Upper

Sarmatian, and influenced by palaeogeographic

changes from this period (the regression of the

Sarmatian Sea towards south, the high altitudes of

Eastern Carpathians), a drop in MAT (with 1.5C),

MAP and WMT was observed.

Palaeoclimatic estimation of Pontian deposits

come from microflora assemblage of South-Western

part of Romania. Therefore the values calculated for

these deposits are: MAT of approximately 16.4

17.2 C, MAP coexistence interval of 1162-1355

mm, CMT value was 5.8C and WMT about 26C.

Acknowledgements

The authors thank Dr. Torsten Utescher(Steinmann Institute, Bonn University) for providing

values of coexistence intervals for palynological

taxa used in palaeoclimatic estimation presented in

this paper. The authors also wish to thank to Dimiter

Ivanov for improving the first draft of this

manuscript.

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Received at: 16. 11. 2011Revised at: 10. 02. 2012

Accepted for publication at: 14. 02. 2012Published online at: 15. 02. 2012

Tabara_ Chirila _PALAEOCLIMATIC ESTIMATION FROM MIOCENE OF ROMANIA, BASED ON PALYNOLOGICAL DATA

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